Zircon U-Pb age and geochemical constraints on the origin and tectonic implication of Cadomian (Ediacaran-Early Cambrian) magmatism in SE Turkey

Accepted Manuscript Zircon U-Pb Age and Geochemical Constraints on the Origin and Tectonic Implication of Cadomian (Ediacaran-Early Cambrian) Magmatism in SE Turkey Melahat Beyarslan, Yu-Chin Lın, A. Feyzi bingöl, Sun-Lin chung PII: DOI: Reference:

S1367-9120(16)30259-0 http://dx.doi.org/10.1016/j.jseaes.2016.08.006 JAES 2783

To appear in:

Journal of Asian Earth Sciences

Received Date: Revised Date: Accepted Date:

25 February 2016 4 August 2016 9 August 2016

Please cite this article as: Beyarslan, M., Lın, Y-C., Feyzi bingöl, A., chung, S-L., Zircon U-Pb Age and Geochemical Constraints on the Origin and Tectonic Implication of Cadomian (Ediacaran-Early Cambrian) Magmatism in SE Turkey, Journal of Asian Earth Sciences (2016), doi: http://dx.doi.org/10.1016/j.jseaes.2016.08.006

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Zircon U-Pb Age and Geochemical Constraints on the Origin and Tectonic Implication of Cadomian (Ediacaran-Early Cambrian) Magmatism in SE Turkey

Melahat BEYARSLANa* , Yu-Chin LINb, A.Feyzi BİNGÖL a, Sun-Lin CHUNG b,c

a

Deparment of Geological Engineering, Firat University, Elazığ, Turkey

b

Department of Geosciences, National Taiwan University, Taipei, Taiwan

c

Institute of Earth Sciences, Academia Sinica, Taipei, Taiwan

* Corresponding author: Assoc.Prof. Melahat BEYARSLAN E-mail: [email protected]

(version of Feb. 24, 2016; to be submitted to JAES Spec. Issue)

1

Abstract The Bitlis-Pütürge Massifs and Derik volcanics that crop out in the Southeast Anatolian Belt are parts of the Cadomian domain in Anatolia where relicts of the oldest continental crust of Turkey are exposed. The Bitlis-Pütürge Massifs contain a Neoproterozoic basement, with overlying Phanerozoic rocks that were imbricated, metamorphosed and thrust over the edge of Arabia during the Alpine orogeny. The basement consists mainly of granitic to tonalitic augen gneisses and metagranites, associated with schists, amphibolites and paragneisses. Based on whole-rock geochemical data, the augen gneisses are interpreted to have protoliths crystallized from subduction zone magmas. This study conducted the first zircon dating on two augen gneisses that gave

206

Pb/238U dates of 551 ± 6 and 544 ± 4 Ma, interpreted as the

formation ages of the Pütürge Massif, broadly coeval to those of the Bitlis metagranites and the Derik volcanics that occurred from ca. 581 to 529 Ma (the Ediacaran-early Cambrian). The ɛHf(t) values (+1.2 to -5.3) of the dated zircons, with crustal model ages (T DMC) from 1.4 to 1.8 Ga, indicate that formation of the Pütürge Massif involves an older, most likely the Mesoproterozoic, continental crust component. Similar to the Bitlis-Pütürge gneisses, coeval basement rocks are widespread in the Tauride-Anatolide platform (e.g., the Menderes Massif). All these dispersed Cadomian basement rocks are interpreted as fragments of the EdiacaranEarly Cambrian continental arcs bordering the active margin of northern Gondwana.

Keywords: Cadomian, gneisses, zircon U-Pb and Hf isotopes, Pütürge, SE Anatolia

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1. Introduction Turkey is located in the middle of the Alpine–Himalayan orogenic belt, which resulted from the closure of different branches of the Tethyan Ocean, along with the amalgamation of two major continents, Gondwana in south and Laurasia in north. Many Late Neoproterozoic to Early Paleozoic (600 to 500 Ma) blocks within the Alpine–Himalayan orogenic belt (Fig. 1a) were generated by the Ediacaran-Cambrian arc-type magmatism or so-called the Cadomian events, as suggested by paleomagnetic data, distribution of fossils, detrital zircon geochronology and zircon U-Pb age data of magmatic rocks and gneisses (e.g., Nance and Murphy, 1996; Fernández-Suárez et al., 2000, 2002; Stampfli, 2000; Nance et al., 2002; Neubauer, 2002; Keppie et al., 2003; Murphy et al., 2004; Winchester et al., 2006; Linnemann et al., 2007; Nance et al., 2008; Ustaömer et al., 2009; 2012; Cocks and Torsvik, 2011; Stampfli et al.,2013; Gürsu et al., 2015; von Raumer et al., 2015; Avigad et al., 2016). The Neoproterozoic-Cambrian time frame was dominated by the growth of the Gondwana Supercontinent that resulted from a long-lived orogenic construction, starting from the breakup of Rodinia (~870–800 Ma) to the final amalgamation of rifted blocks in Cambrian times (e.g. Dalziel, 1991; Meert, 2003; Boger and Miller, 2004; Collins and Pisarevsky, 2005; Cawood, 2005; Cawood and Buchan, 2007; Li et al., 2008; Torsvik and Cocks, 2013; Nance et al., 2014). The terminal assembly that occurred - older than or about 600 Ma was achieved through complex accretion of various continental blocks involving a prolonged collisional assembly between East and West Gondwana (Meert, 2003; Collins and Pisarevsky, 2005; Meert and Lieberman, 2008; Stampfli et al., 2013) and development of subduction systems along the margins of the Gondwana supercontinent, e.g., the Terra Australis Orogen and the North India Orogen (Boger and Miller, 2004; Cawood, 2005; Murphy et al., 2011). In this paper, we report the first zircon U-Pb ages of augen gneisses from the Pütürge Massif, an important albeit less studied component of the Southeast Anatolian Belt as part of the 3

Cadomian domain in Turkey. We then combine regional literature with our field, geochemical, geochronological data obtained from the Bitlis-Pütürge metamorphic Massifs and associated Derik volcanics in the Arabian Plate to interpret the Ediacaran-Terreneuvian tectonic evolution of the South Anatolian Belt in Turkey, with further implications for the Cadomian events related to the formation and subsequent breakup of the Gondwana Supercontinent.

2. Geological Background 2.1. Bitlis-Pütürge Massifs The Late Neoproterozoic-Cambrian basement rocks of Turkey are generally interpreted as the dispersed fragments of the Cadomian active margin (Ustaömer et al., 2009, 2012; Gürsu et al. 2015). Recent efforts to understand the Cadomian basement in Turkey emphasize dating of metamorphosed magmatics (granites and gabbros) and gneissic rocks and provenance analysis of Paleozoic sedimentary units (e.g., Ustaömer et al., 2009, 2012; Zlatkin et al., 2013; Yılmaz-Şahin et al, 2014; Gürsu et al., 2015; Candan et al., 2015; Avigad et al., 2016). Gondwana-derived Late Proterozoic/Early Paleozoic units in Turkey mainly crop out in five separate Alpine tectonic units; (i) the Istanbul-Zonguldak Terrane (IZT), (ii) the TaurideAnatolide Platform (TAP),(iii) Menderes Massif, (iv) Bitlis-Pütürge Massifs and (v) the South Anatolian Autochthone Belt (Fig. 1b). The Bitlis-Pütürge metamorphic Massif represents one of the metamorphic Massifs of southeast Anatolia (Fig.2); including the Malatya, Keban, Engizek, and Binboga Massifs. The Bitlis and Pütürge Massifs are regional-scale allochthonous units that show similar stratigraphic successions. They may be interpreted as parts of a once-united giant tectonostratigraphic unit that has been disrupted and fragmented during orogeny (Yılmaz and Yiğitbaş, 1991). They comprise a high grade metamorphic lower unit and a lower grade 4

metamorphic cover as the upper unit forming an envelope around the lower unit (Göncüoğlu and Turhan, 1984; Erdem, 1994; Erdem and Bingöl, 1995) (Figs. 3a,b). The high grade metamorphic lower units of the two Massifs are similar and are composed of granitoid gneiss (augen gneiss) ranging in composition from quartz diorite, tonalite to granodiorite, various schists, amphibolites, and meta-granites. The augen gneisses are the lowermost unit of the Bitlis-Pütürge Massifs (Göncüoğlu and Turhan, 1984; Erdem, 1994; Erdem and Bingöl, 1995). The augens consist of K-feldspar reaching up to 10-15 cm long (Fig 4a) There are some eclogite relicts in the central part at Mt. Gablor (Okay et al., 1985) and in the Kesandere valley in the easternmost of the Bitlis Massif (Oberhänsli et al., 2014) in the high grade lower unit rocks. The Kesandere eclogites formed during the middle Late Cretaceous, whereas a Pan-African age was assumed for the Mt. Gabor eclogites (Okay et al., 1985; Oberhänsli et al., 2014). The Mt. Gablor eclogitic bodies were produced by eclogitic metamorphism of the subducted plate during the Ediacaran-early Cambrian southward subduction and exhumed into the high-grade metamorphic units at the final stage of subduction, whereas the Kesander eclogites were formed by metamorphism of the subducted plate during the Late Creteceous northward subduction and exhumed into the other units at the final stage of subduction (Oberhänsli et al., 2012; 2014). The schists, composed of biotite, muscovite, garnet and amphibole, are crosscut by amphibolites (Fig.4b) and metagranites. The meta-granites cut the augen gneisses, amphibolites and schists, but they do not cut the Permian formations, thus, they should have formed before Permian time (Erdem and Bingöl, 1995). According to Göncüoğlu and Turhan (1984), the metagranites are unaffected by the predominent

regional metamorphism. Regardless of variable age data, Göncüoğlu and

Turhan (1984) suggested a Middle Devonian–Late Permian crystallisation age for the metagranitic rocks based mainly on the reported field evidence that some of the granites cut Devonian meta-sedimentary formations but never cut the Mesozoic cover (Figs.3a, b).

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The lower unit rocks underwent high grade metamorphism related possibly to the final amalgamation of exotic terranes with northeastern Gondwana or to the development of a subsequent subduction zone along the Gondwana margin (Collins and Pisarevsky, 2005). The lower unit is overlain by muscovite schist that contain mid-Devonian fossils with kyanite bearing quartzite lenses, garnet staurolite micaschist and Permian recrystallized limestones. There are some andesitic and dacitic dykes belonging to the Middle Eocene Maden Complex within the Permian recrystallized limestones (Yıldırım, 2010). In this respect, as well as in the degree of metamorphism of the lower unit, the Bitlis-Pütürge Massifs resemble the Menderes Massif.. The Triassic unit of Bitlis Massif, which is missing in Pütürge Massif consists of recrystallized limestones and calc-schists grading upward into metashales, metatuffs, metadiabases and metabasalts and finally metaconglomerates, metamudstones and shales (Oberhansli et al., 2011). The Pütürge metamorphics depositionally overlain by the Middle Eocene Maden Complex whereas the Bitlis Massif overlain by the Middle Miocene to Quaternary volcanics in the North. All these rocks are exposed by thrusts onto the neoautochthonous Arabian Platform and Neo-Tethyan ophiolites along its southern contacts (Perinçek, 1980; Perinçek ve Özkaya, 1981; Yazgan, 1983; 1984; Michard vd. 1984; Aktaş ve Robertson, 1984; Yazgan ve Chessex, 1991; Yılmaz, 1993; Yılmaz vd., 1993;Yiğitbaş ve Yılmaz, 1996; Yılmaz ve Yıldırım, 1996).The lower unit rocks and upper unit were metamorphosed under greenschistfacies conditions during Upper Cretaceous (Yazgan and Chessex, 1991; Erdem and Bingöl, 1995). 2.2 Derik area Derik area (Mardin) is located along the northernmost margin of the Arabian Plate. The basal section of the Derik area consists of non-metamorphosed volcanic rocks, conglomerates and fine/coarse sandstones. This succession is known as the “Infracambrian of SE Anatolia” (Ketin, 1966). The basal detrital was reported first by Kellogg (1960). “Derik volcanics”

6

composed of non-metamorphic succession of basaltic lavas and subordinate volcanoclastics, however the base of it is not exposed (Göncüoğlu and Kozlu, 2000). Overlying deposits include, in ascending order, conglomerates, a limestone horizon, and a redbed type succession. . The lack of biostratigraphic data and rapid lateral variations characterize the first depositional sequence, which is coeval with the ultimate Pan-African/Cadomian postcollisional events that affected northern Gondwana (Ghienne et al., 2010). The volcanic rocks are divided into three sub-units by Gürsu et al. (2015). (a) A thick sub-unit composed of early stage andesitic lavas and rhyolite with rare siltstone/sandstone intercalations. Rhyolites associated with pyroclastic rocks are observed within early-stage andesitic rocks, (b) late stage andesitic rocks and (c) pyroclastic rocks (agglomerates/volcanic breccias).

3. Petrography 3.1. Augen gneisses The augen gneisses from Pütürge Massif are coarse- to very coarse-grained rocks composed of microcline + quartz + red brown biotite + muscovite ± zircon ± apatite ± ilmenite mineral assemblage. The augen gneisses also contain chlorite ± green biotite ± albite ± epidote mineral assemblage.. This second mineral assemblage should belong to the retrograde phase that effect the lower and upper units during Late Cretaceous. The K- feldspar augens mostly consist of single crystals of K-feldspar. The augens are pink to milky white, and can reach up to 10-15 cm long in the fine- to medium-grained granoblastic and lepidoblastictextures. Lepidoblastic matrix composed of fine to coarsegrained quartz, plagioclase and K-feldspar and medium- to coarse-grained biotite, with rare small muscovite plates. Inclusions of quartz, muscovite, zircon, and minor biotite are common. The lepidoblastic texture may be separated from augen of granoblastic textures or in direct contact with them.-The augen gneisses from Bitlis are plagioclase-augen gneisses

7

(Göncüoğlu and Turhan, 1984). They are coarse grained rocks composed of quartz, oligoclase, biotite, garnet, muscovite. The augen consists of single crystals of plagioclase.All metagranites have a well-preserved igneous mineralogy but they show granoblastic andlepidoblastic and mylonitic textures. The metagranites mainly consist of plagioclase, Kfeldspar, quartz and biotite, with minor muscovite ± amphibole ± muscovite ± zircon ± titanite ± garnet ± opaque minerals. The proportion of these minerals has shown changes in different lithologies. In the QAP (Quartz-Alkali feldspar-Plagioclase) ternary diagram (Fig.5; Streckeisen, 1976), the augen gneisses and metagranites plot in the tonalite to monzo-granite fields.

3.2. Derik volcanics (Gürsu et al., 2015) Based on their mineralogical composition and textural characteristics, the Derik Volcanics in the Derik (Mardin) area can be divided into three lithological units, namely andesite, rhyolite and mafic dykes. Andesites are porphyritic, with abundant phenocrysts set in an originally partly glassy, now devitrified fine groundmass consisting mainly of microcrystalline plagioclase and opaque minerals. The phenocrysts are mainly characterized by plagioclase, amphibole and minor pyroxene and biotite. The rhyolites display porphyritic texture. Phenocryst mineral phases include quartz, sanidine, sodic plagioclase, with occasional hornblende, while zircon, apatite, titanite and pyrite are accessory minerals.

Plagioclase phenocrysts are lath- or tabular-shaped, euhedral to

subhedral, ranging up to 1 cm in size and show zoning and albite-type polysynthetic twinning. Alkali feldspar phenocrysts are rare in most samples. Quartz is commonly subhedral, with straight edges. This quartz also occurs in the matrix, filling the interstitial spaces. The groundmass is fine-grained anhedral granular and is composed of quartz, alkali feldspar and plagioclase with intergranular opaques, chlorite and accessory apatite and zircon.

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4. Analytical Methods Twelve representative samples of metamorphic rocks from the Pütürge Massif have been analyzed for their major and trace element composition (Table 1). Four of these samples were analyzed (13TK-51 to -54) at the Shen-su Sun Memorial Lab of Department of Geosciences, National Taiwan University, where major elements were measured by X-ray fluorescence (XRF) techniques on fused glass beads using a Rigaku ® RIX-2000 spectrometer and trace elements were measured by the inductively coupled plasma-mass spectrometry (ICP-MS) using an Agilent 7500cs equipment. The detailed analytical procedures were the same as those reported in Lin et al. (2012). The other eight samples (P132-P168) were analyzed at the ACME Analytical Laboratories, Vancouver, Canada, using ICP emission spectrography for major elements and some trace elements (Ba, Nb, Ni, Sr, Sc, Y and Zr), and ICP-MS for other trace elements including rare earth elements. Two augen gneiss samples, 13TK51 and 13TK54, were subjected to in situ zircon U–Pb dating and Lu-Hf isotope analysis (Tables 2,3). Euhedral to subhedral zircons with few cracks and inclusions were picked out under binocular with hands, and then mounted on the epoxy resin and polished for cathodo-luminescence (CL) imaging that was taken for observing the internal structure of each zircon grain and selecting suitable position for isotope analysis. Zircons were first dated by using the laser ablation ICP-MS facilities at Department of Geosciences, National Taiwan University. The detailed analytical methods with analytical precision can be found in Chiu et al. (2009) and Shao et al. (2015). Zircon Lu-Hf isotopes were measured using a Neptune multi-collector ICP-MS equipped with a Lambda Physik COMpex UV-193 laser-ablation system at the Institute of Geology and Geophysics, Chinese Academy of Sciences in Beijing, China. Detailed analytical procedures are described by Wu et al. (2006). Lu-Hf isotopic calculations are made with following equations: 9

-11

λ Lu-Hf = 1.86 × 10 y (Scherer et al., 2001) Hf(T)=[( Hf/ Hf)Sample /( 176

(

176

177

177

T

Hf/ Hf)Sample =( 177

176

T

177

176

177

T

4

Hf/ Hf)CHUR -1] x 10 (Patchett and Tastumoto, 1981)

0 176

177

0

λT

Hf/ Hf)Sample -( Lu/ Hf)Sample x (e -1); ( 176

T

176

177

0 176

Hf/ Hf)CHUR -(

177

0

λT

Lu/ Hf)CHUR x (e -1)

176

Hf/ Hf)CHUR =0.282772; ( Lu/ Hf)CHUR =0.0332 (Blichert-Toft and Albarede, 1997)

(

176

Hf/ Hf)DM=0.28325; ( Lu/ Hf)DM =0.0384 (Nowell et al., 2000; Griffin et al., 2000)

176

177

177

Hf/ Hf)CHUR =(

(

177

0

176

0

177

(176Lu/177Hf)mean crust =0.015 (Griffin et al., 2000) f CC = (0.015/0.0332)-1 = -0.5482 ; f DM = (0.0384/0.0332)-1 = 0.1566

The data of Bitlis gneisses and metagranites (Ustaömer et al., 2012) and Derik volcanics (Gürsu et al., 2015) were compared with our results from Pütürge gneisses in this study.

5. Whole-Rock Geochemistry The augen gneisses of the Pütürge Massifs display similar range of compositions from tonalite to monzogranite with the rocks from Bitlis Massifs and Derik volcanics. The most common rocks are monzogranite (Fig. 5), and their SiO2 content ranging from 57.3% to 71.6%. They contain 1.27-4.11%K2O and 1.53-5.28%Na2O. Since the major element, and especially alkali elements, classification is dubious due to alteration of the Pütürge gneisses, immobile trace elements have been used to constrain their tectonic environment of formation. Chondrite-normalized REE patterns of the augen gneisses -of Pütürge Massifs show similar trends with metagranites of Bitlis Massifs and volcanics of Derik. The augen gneisses of Pütürge Massif show an enrichment of LREE (light rare earth elements) in respect to HREE (heavy rare earth elements; LaN/YbN = 5.21-15.37) and relatively flat HREE (GdN/YbN = 1.55-2.02). (Figs. 6a,b). The nature of the negative Eu anomalies suggests that the rocks evolved by fractional crystallization of plagioclase or that they originated from partial melting in the presence of feldspar in the source. In the primitive mantle-normalized incompatible element spidergrams (element ordering after Thompson et al., 1984), the augen gneisses of Pütürge Massif display overall LILEs (Large

10

Ion Litophile Elements)-enriched patterns, with negative Nb, Ta, Sr, P, and Ti and positive Rb and Th anomalies (Figs. 6c, d). Enrichment in Large Ion Lithophile Elements (LILEs) and depletion in High Field Strength Elements (HFSEs) suggest that these rocks originated above a subduction-related zone. Depletion in Ti and Sr could be related to the titanomagnetite and feldspar (with Eu anomaly) fractionation. Based on Co vs Th of Hastie et al. (2007) diagram, they classify as high-K calc-alkaline alkaline and shoshonitic granites (Fig. 7a). In the discrimination diagrams for differientiated rocks, i.e., Zr vs. Nb/Zr(n) (ppm) diagram of Thieblemont and Tegyey (1994), the augen gneisses of Pütürge Massif plot on the boundary between the subduction-related field and the collision-related field. However, rocks from Bitlis Massif and Derik plot within the subduction to collision-related fields. The other three discrimination diagrams for granites after Pearce et al. (1984), i.e., Yb vs. Ta, Y+Nb vs. Rb, and Yb+Ta vs. Rb, suggest that all the studied rocks were volcanic arc granites. On Schandl and Gorton (2002) diagrams (e.g., Th/Yb vs Ta/Yb) gneisses show characteristics of the volcanic rocks generated in active continental margin (ACM) (Figs. 7b,f).

6. Zircon U-Pb Ages Two samples from the Pütürge augen gneiss were selected for in-situ zircon U–Pb dating and Lu-Hf isotopic analysis. In CL images, the zircons are mostly euhedral, colorless to pale brown, and show oscillatory zoning suggesting an igneous origin (Fig. 8). The augen gneiss samples of 13TK51 and 13TK54 show variable Th/U ratios of 0.08–0.87 and 0.09-0.57, respectively (Table 2). This high Th/U ratio is consistent with an igneous origin for the analyzed zircons. The weighted mean

206

206

Pb/238U ages of 13TK51 range from 573 to 529 Ma, having a

Pb/238U age of 551 ± 6 Ma (n=21, MSWD=3.7, Fig. 9a). The

206

Pb/238U

ages of 13TK54 range from 556 to 528 Ma, having a weighted mean 206Pb/238U age of 544 ± 4 11

Ma (n=21, MSWD=1.4, Fig. 9b). These two ages interpreted the time of zircon crystallization. Zircon in-situ Lu-Hf isotopes were also analyzed for two Pütürge augen gneiss samples in the same spots of U-Pb analysis. They have similar 0.075 and 0.001–0.003 (Table 3). The

176

176

Yb/177Hf and

176

Lu/177Hf values of 0.020–

Lu/177Hf values are close to or less than 0.002,

indicating that there is no significant accumulation of radiogenic Hf after the formation of these zircons. The initial

176

Hf/177Hf ratios for the Pütürge gneisses range from 0.2823 to

0.2825 (εHf (t) = -5.3 to +1.2) with the crustal model ages range from 1.8 to 1.4Ga, suggesting involvement of older continental crust in magma genesis (Figs. 10a, b). The Hf isotopic composition of Pütürge augen gneiss is similar to the other Cadomian intrusions (Ustaomer et al., 2012; Zlatkin et al., 2013; Avigad et al., 2016) including the granites and metagranite from Bitlis Massif (εHf (t) = -2 to -1 and -5 to -4), the orthogneisses from Menderes Massif (εHf (t) = -5 to +2), and the igneous rocks from Tauride Massif (εHf (t) = -6 to +3).

7. Discussion

The geochemical data of the rocks in this study were plotted on various major and trace element tectonic discrimination diagrams. In the Co versus Th diagram of Hastie et al., (2007) (Fig.7a), the augen gneisses of Pütürge Massif fall in the high-K calc-alkaline and shoshonitic field. The augen gneisses are compared with volcanic arc granite (VAG) syn-collision granite (syn-COLG),within plate granite (WPG) and orogenic related granite (ORG). In Y+Nb versus Rb, Ta versus Yb diagrams and Yb+Ta versus Rb of Pearce et al. (1984) (Figs. 7b,c,d), augen gneisses of Pütürge Massif fall in the volcanic arc granite (VAG) field; the subduction-related tectonic setting is also supported by the distinct negative Nb, Ta, P and Ti anomalies in

12

primitive mantle normalized trace elements diagrams (Figs. 6c,d). In the Zr versus Nb/Zr n diagram (Fig. 7e), augen gneisses samples fall between the subduction-related field and the collision related field. In all diagrams, the Pütürge augen gneisses fall into the same fields with meta-granites of Bitlis Massif and Derik volcanics (Figs. 7 b-e). Gorton and Schandl (2000) suggest a tectonic discrimination based on the concentrations and ratios between Th, Ta and Yb. In this classification, the Th/Ta values of the Pütürge augen gneiss samples (522.34, with an average of 14.52) are similar to those of felsic to intermediate volcanic rocks of active continental margins (Th/Ta between 6 and 20). In the Th/Ta versus Yb diagram idealized by Gorton and Schandl (2000), the samples plot mostly in the active continental margin field (Fig. 7f). In a similar manner, the La/Nb ratios of 1.07-4 (average 2.49) are remarkably within the range of those of arc magmas (1.3-6), in comparison to within-plate magmas in which this ratio is much lower (around 0.8; Rudnick, 1995). The new zircon crystallisation ages of 551±6 Ma and 544±4Ma (Ediacaran–Early Cambrian) constitute the first U/Pb radiometric dates of augen gneisses from the Pütürge Massif in SE Turkey. The combined major-element, trace-element suggest the existence of Andean type arc-related magmatism. Whereas zircon dating is crucial in identifying the protolith age for granitic rocks that were subjected to high-grade metamorphism, Hf isotopes can be used to determine the nature of the protolith (Zheng et al., 2004, 2006; Belousova et al., 2006; Wu et al., 2007). A depletedmantle model age (TDM) for the magmatic host rock of a given zircon is calculated using the measured

176

Hf/177Hf and

176

Lu/177Hf of the zircon. Calculation results give a minimum age

for the source rock of the host magma. A more realistic “crustal” model age (T DMC) is calculated by assuming that the source rocks of the magma had the

176

Lu/177Hf ratio of the

average continental crust. Large differences in the Hf-isotope composition of zircon grains of similar age can be explained either by mixing crust- and mantle-derived magmas (Griffin et

13

al., 2002; Belousova et al., 2006), or by melting of a heterogenous crustal sources (Ali et al., 2015). Zircon typically contains tens of ppm of Lu but ~1% Hf (Hiess et al., 2009), thus it is the major reservoir for Hf in granitoids (Hoskin and Schaltegger, 2003; Hiess et al., 2009). The very low 176Lu/177Hf ratios of zircons result in their present-day Hf isotopic compositions approximating that of magmas from which the zircons crystallized (Kinny and Maas, 2003). These zircons have 176Hf/177Hf ratios consistent with evolution in a reservoir with 176Lu/177Hf, i.e. continental crust (low

176

Lu/177Hf) or depleted mantle (high

176

Lu/177Hf), or reflect a

mixture of melts from older crust and depleted mantle (Amelin et al., 2000; Chauvel and Blichert-Toft, 2001; Hiess et al., 2009). The Pütürge gneissic rocks yieded εHf (t) values of 5.3 to +1.2) with the crustal model ages range from 1.8 to 1.4 Ga, suggesting involvement of older continental crust in magma genesis. The elemental variations from our study reveal that the studied rocks may have been derived from crust-derived (lower crustal) magmas and followed by limited effects of the assimilation-fractional crystallization (AFC) process of the middle and/or upper continental crustal source. Their negative εHf(t) and older TDM ages are clearly restricted a juvenile mafic source. On the primitive mantle normalized multi-element diagrams, augen gneisses display relative enrichment in HFSE and REE and indicate that they may have been derived from mafic lower continental crustal sources followed by mixing of middle or upper continental crustal materials during the magma emplacement. The crustal modal ages varying from 1.4 to 1.8 Ga in augen gnesises are older than U–Pb crystallization age of the studied samples and show either a contamination of the lower crustal source with older material or older source. Our new results can also be compared with previous evidence of dated Late PrecambrianEarly Cambrian magmatic rocks in Turkey and in Iran. The nearest of these units to the Pütürge gneisses are the Ediacaran–Early Cambrian meta-granites in Bitlis Massif. Ustaömer et al. (2009 and 2012) obtained a

207

Pb/206Pb single-zircon age of 545.5±6.1 Ma and

14

531.4±3.6 Ma from Mutki meta-granites and an age of 572±4.8 Ma from Doğanyol metagranites in the Bitlis Massif. The Mutki granite yielded ɛNd(t = 545) values of –1.88 and –1.237, whereas granitic dikes yielded ɛNd(t = 532) values of –2.88 and –2.03 (Ustaömer et al., 2009), for which a TDM (Nd) model age of 1.3 Ga was estimated. Doğruyol meta-granite yielded ɛNd(t = 567) of

–5.13 and –4.11 (Ustaömer et al., 2012).The206Pb/238U crystallization ages of the meta-

granitic intrusions within the high-grade metamorphic basement of

the central and the

southern Menderes Massif show that they were formed during the Late Neoproterozoic, between 543 and 554 Ma (Hetzel and Reischmann, 1996; Oberhänsli et al., 1998, 2010; Loos and Reischman, 1999, 2001; Gessner et al., 2004; Candan et al., 2001; 2011; Koralay et al., 2012; Gürsu, 2016). These Cadomian igneous rocks yielded ɛHf(t) values of -5 and +2 with corresponding Hf depleted mantle model ages (Hf-TDM) of 1.2–1.6 Ga (Zlatkin et al., 2013;Avigad et al, 2016). Cadomian late to post-collisional I-type granitic rocks mainly intruded Tauride-Anatolite Platform (N and S of Afyon) and were cut by abundant tholeiitic dikes between 560 and 545 Ma (Gürsu and Göncüoğlu, 2005, 2008) and South Anatolian Autochthone Belt (Derik volcanics) (Gürsu et al., 2015). The Derik volcanics have 581 ± 4 Ma and 559 ± 3 Ma for the early and late-stage andesitic rocks, 570 ± 2 Ma, 572 ± 2 Ma, and 575 ± 4 Ma for the rhyolites (Gürsu et al. 2015) The granitoids of the Cadomian Orogeny can be traced eastward into Iran, Central Iran (ca. 599-525 Ma, Ramezani and Tucker, 2003; Hassanzadeh et al., 2008; Shafaii Moghadam et al., 2015), the Sanandaj-Sirjan Zone ( ca. 596-540Ma, Hassanzadeh et al., 2008; Jamshidi Badr et al., 2013; Shafaii Moghadam et al., 2015). U-Pb zircon geochronolgy of various orthogneiss in Turkey and in Iran Neoproterozoic basement yielded ~599-525Ma ages. A cumulative zircon U-Pb ages of all availabe data for Cadomian igneous rocks of the Turkey and Iran defines a concentration in a narrow time interval about 550Ma (Yılmaz Şahin et al., 2014; Shafaii Moghadam et al., 2015; Avigad et al., 2016).

15

Hf and Nd isotopic data and the nagative ɛHf(t) and ɛNd values from Cadomian-Early Cambrian igneous rocks of the Turkey, except Derik volcanics, and Iran thus indicate the involvement of preexisting crust in their generation, with Hf model ages of 1.2–1.8 Ga. Gürsu et al., (2015) suggest that the average positive ɛNd(T) data of the Derik volcanik indicate that earlystage andesites and mafic dykes were dominantly generated from subduction-enriched mantle-derived magmas but rhyolites and late-stage andesites have lower positive ɛNd(T) values than early-stage andesites and mafic dykes and clearly indicate the effects of contamination with crustal source in their genesis.There are many Cadomian-Avolian Terranes in Europe, in Asia and in America (Fig. 11). There is indeed general agreement that an active Andean-type continental margin, featuring magmatic arcs and back-arc basins, formed the entire northern margin of Gondwana, with subduction beginning at about 760Ma and ending diachronously with the development of transform fault systems (e.g. Neubauer, 2002; Stampfli et al., 2002; Von Raumer et al., 2002; Murphy et al., 2004). The Neoproterozoic-Cambrian time frame was dominated by the growth of the Gondwana Supercontinent that resulted from a long-lived history of orogenic construction, starting from the breakup of Rodinia (870–800 Ma) to the final amalgamation in Cambrian times (e.g. Dalziel, 1991; Meert, 2003; Boger and Miller, 2004; Collins and Pisarevsky, 2005; Cawood, 2005; Cawood and Buchan, 2007; Li et al., 2008; Torsvik and Cocks, 2013; Nance et al., 2014). The terminal assembly of Gondwana largely occurred older than or about 600 Ma and was achieved through accretion of various continental blocks both involving prolonged collisional assembly of East and West Gondwana continents (Meert, 2003; Collins and Pisarevsky, 2005; Meert and Lieberman, 2008) and development of subduction systems all along the margins of the Gondwana supercontinent (Terra Australis Orogen and North India Orogen, Boger and Miller, 2004; Cawood, 2005; Cawood et al., 2007; Murphy et al., 2011). The assembly of the Gondwana supercontinent during the late Neoproterozoic involved

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closure of the intervening Neoproterozoic oceans (Collins et al., 2007) and subduction of a substantial volume of oceanic lithosphere along a number of convergent margins (Santosh et al., 2009). Prior to the breakup, the Gondwana supercontinent had an active subduction margin along the Pacific side (Cawood, 2005), whereas on the northern side there was a passive margin (Windley, 1992; Şengör, 1984). This passive margin also occurred in Iran (Shafaii Moghadam et al., 2015), and in Turkey. In Turkey, the Cadomian fragments mainly occured in three separate Alpine tectonic units; the Istanbul-Zonguldak Zone (Bolu Massif, 576–565 Ma, Chen et al., 2002; Ustaömer et al., 2005), the Tauride–Anatolian Block (570– 540 Ma, Gürsu et al., 2004; Gessner et al., 2004; Gürsu and Göncüoglu, 2006; Candan et al., 2015), the Bitlis Massif of SE Turkey (545–531 Ma from Ustaömer et al., 2009 and 572 Ma from Ustaömer et al., 2012), Pütürge augen gneisses of SE Turkey (551-544 Ma, this study) and South Anatolian Autochthone Belt (Derik volcanics, Gürsu et al., 2015). Subduction of Proto-Tethys oceanic lithosphere beneath the Gondwana was responsible for arc magmatism at the northern edge of Gondwana during the Late Proterozoic to Early Cambrian (Ramezani and Tucker, 2003; Nadimi, 2007). Subduction beneath the active margin of Gondwana is suggested to have ceased around 450–400 Ma, due to continental or oceanic plateau collision (Ustaömer et al., 2009). After this collision, Ordovician rifting opened Paleotethys, separating slices of N Gondwana from the Southeast Anatolian Massifs (BitlisPütürge) and Derik volcanics and they were re-amalgamated in Oligo-Miocene times. The basement rocks of the Bitlis-Pürtürge Massifs were strongly deformed and metamorphosed under amphibolite facies conditions, but eclogite relicts are also present during the Cadomian orogeny. Metamorphic domains in zircon crystals seem to date the last Cadomian metamorphism (529 ± 5 Ma, Ustaömer et al., 2012). This was possibly related to a collision during the final amalgamation of exotic terranes with northeast Gondwana, or to the

17

development of a subsequent subduction zone along the margin Gondwana (Collins and Pisarevsky, 2005).

8. Conclusion Augen gneisses and metagranites of the Bitlis-Pütürge Massifs and non-metamorphic Derik volcanics have late Neoproterozoic (Ediacaran) to early Cambrian (Terreneuvien) ages. They show geochemical characteristics suggesting an origin from active margin magmatism that we infer to have occurred in the northern margin of Gondwana. In this study, we report for the first time zircon U-Pb ages (551 ± 6 and 544 ± 4 Ma) of two augen gneisses form the Pütürge Massif. Zircon εHf(t) values of these augen gneisses suggest the involvement of older continental crust in magma genesis. The Hf model ages suggest that this older crust is of the Mesoproterozoic, ~1.4 to 1.8 Ga. Augen gneisses and meta-granites of the Bitlis-Pütürge Massifs. Together with the Derik volcanics and other coeval basement rocks in the Tauride– Anatolian block (Turkey) were part of Gondwana until the Paleozoic, when they separated during Neotethys rifting and then were re-amalgamated in Oligo-Miocene times. The high grade metamorphism of the Lower units of the Bitlis-Pütürge Massifs was possibly related to a collision during the final amalgamation of exotic terranes with northeast Gondwana, or to the development of a subsequent subduction zone along the margin of Gondwana.

Acknowledgments We thank Mustafa Rizeli and Mehmet ERTURK (Firat University) for field assistance, and Chien-Huei Hung, Hao-Yang Lee and Te-Hsien Lin (National Taiwan University) for laboratory assistance. This study was performed under a joint research program supported by Firat University and National Taiwan University. The authors are greatly appreciated to

18

editor and two reviwers for contributions and recommendations that significantly improved the manuscript.

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32

Figure

a

b

Figure 1 a,b

Figure

Figure 2

Figure

Figure 3 a,b

Figure

Figure 4 a,b

Figure

Figure 5

Figure

Figure 6. a,b,c,d

Figure

Figure 7 a,b,c,d,e,f

Figure

Figure 8

Figure

Figure 9 a,b

Figure

Figure 10 a,b

Figure

Figure 11

Table 1 Major and trace elements for augen gneiss samples from Pütürge massif

MnO MgO CaO Na2O K2O P 2 O5

13TK51 71.3 0.51 14.2 2.36 0.02 0.94 1.68 4.75 2.59 0.14

13TK52 60.1 0.87 18.1 8.97 0.13 3.41 1.47 1.53 3.05 0.21

13TK53  63.5 1.19 19.5 1.62 0.03 1.14 2.27 7.42 1.32 0.03

13TK54 67.9 0.63 14.7 4.39 0.04 1.37 1.31 3.27 4.29 0.14

LOI TOTAL

98.5

97.8

98.0

Sc V Cr Mn Co Ni Cu Zn Ga Rb Sr Y Zr Nb Cs Ba La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu Hf Ta Pb Th U

19 39 82 181 5.1 44 5.2 22 21 76 105 34 264 15 0.60 366 39 79 9.2 33 6.6 0.96 6.0 0.96 5.7 1.2 3.3 0.49 3.2 0.45 6.5 1.3 1.2 19 2.5

22 138 111 956 19 59 40 205 23 128 162 40 168 12 8.0 606 35 70 8.4 34 6.3 1.4 6.6 1.1 6.3 1.3 3.7 0.55 3.5 0.53 4.3 0.86 24 10 2.9

10 88 102 197 3.9 55 6.6 0 22 50 208 28 238 17 0.54 163 20 69 8.7 33 5.2 0.88 5.0 0.78 4.4 0.90 2.7 0.40 2.6 0.40 6.2 1.0 1.1 5.0 3.1

SiO2 TiO2 Al2O3 Fe2O3

98.0

P132 57.3 1.46 16.7 6.09 0.08 3.16 6.09 4.45 1.59 0.35 2.51 99.8

P136 70.6 0.57 15.7 2.42 0.02 1.21 0.87 5.28 1.27 0.13 1.14 99.2

P144 71.6 0.62 13.5 2.78 0.02 0.98 1.81 4.35 2.04 0.15 2.07 99.9

P145 67.8 0.61 13.8 4.88 0.02 1.45 1.29 3.34 4.11 0.14 1.84 99.3

P152 67.5 0.53 14.4 3.27 0.02 1.69 1.43 3.18 4.47 0.12 1.98 98.6

P154 69.8 1.42 14.6 2.59 0.02 1.37 1.62 3.13 2.41 0.13 1.47 98.6

P161 70.8 0.52 14.3 2.81 0.02 0.98 1.20 4.67 2.61 0.13 1.27 99.3

P168 69.9 0.49 13.5 2.41 0.05 1.83 2.47 3.19 2.41 0.14 2.53 98.9

19 56 47 282 7.4 22 7.9 29 19 134 124 34 259 13 1.8 875 42 86 10 37 6.6 1.2 6.6 1.0 5.7 1.1 3.1 0.45 2.7 0.40 6.9 0.94 5.8 21 2.6

26 179 292 657 5.8 15 11 42 19 62 250 45 310 26 6.0 350 28 66 9.2 33 6.4 0.96 6.0 0.98 5.4 1.2 3.3 0.46 3.2 0.43 6.2 1.1 4.2 15 2.9

10 54 79 183 5.2 43 18 12 22 75 131 35 213 14 2.9 147 38 76 8.9 32 6.2 1.1 6.4 1.1 5.8 1.2 3.3 0.51 3.2 0.48 5.3 1.0 1.2 17 2.8

12 118 102 179 4.6 68 17 42 21 126 159 32 187 12 1.9 443 27 71 9.1 34 5.8 0.91 6.5 0.83 6.2 1.1 3.0 0.48 3.4 0.52 6.7 1.1 1.4 13 2.9

19 98 131 182 6.5 52 27 17 19 112 151 39 227 12 0.97 287 24 53 8.8 26 6.4 1.2 6.1 1.0 6.1 1.2 3.1 0.47 3.3 0.42 6.2 1.1 1.2 14 2.8

14 59 128 167 6.1 54 29 21 21 114 149 41 201 15 6.9 854 60 69 9.1 33 5.7 0.97 6.3 0.81 6.0 1.2 3.2 0.44 2.8 0.41 6.4 1.0 3.4 21 2.7

11 58 97 195 4.6 48 34 22 20 66 157 38 235 13 0.8 521 45 81 8.7 36 6.6 0.91 6.4 0.92 5.8 1.1 3.4 0.48 2.8 0.44 6.3 0.96 2.4 20 3.1

12 49 87 176 7.4 42 12 46 21 63 208 35 219 16 0.9 381 46 85 9.1 38 6.3 1.2 6.5 0.94 5.4 1.1 3.1 0.43 3.1 0.41 5.7 1.1 1.3 18 3.0

17 96 59 162 8.9 39 11 19 19 76 164 34 149 17 6.3 201 27 70 8.9 34 6.1 0.98 6.2 1.1 5.2 0.96 2.9 0.52 3.2 0.53 6.4 1.1 2.2 8.0 2.7

Table 2 Zircon U–Pb LA‐ICP‐MS data of the Pütürge augen gneisses Spot

U (ppm)

Th/U

U‐Th‐Pb ratios 207

Pb/235U

1σ

206

Pb/238U

1σ

207

Pb/206Pb

Ages (Ma) 1σ

208

Pb/232Th

1σ

206

Pb/238U

207

Pb/206Pb

1σ

1σ

207

Pb/235U

1σ

Inferred Age

1σ

13TK51 (wt. Mean age =551±6 (2σ), n=21) 13TK51‐01

546

0.10

0.72306

0.01039

0.08727

0.00107

0.06010

0.00038

0.02367

0.00079

539

6

607

13

552

6

539

6

13TK51‐02

375

0.21

0.72249

0.01075

0.08553

0.00106

0.06127

0.0004

0.02582

0.00086

529

6

649

14

552

6

529

6

13TK51‐04

432

0.11

0.72370

0.01077

0.08759

0.00108

0.05993

0.00039

0.02466

0.00089

541

6

601

14

553

6

541

6

13TK51‐05

638

0.30

0.73391

0.01063

0.08775

0.00108

0.06066

0.00039

0.02547

0.00089

542

6

627

13

559

6

542

6

13TK51‐06

553

0.50

0.71782

0.01064

0.08586

0.00106

0.06065

0.00040

0.02623

0.00094

531

6

627

14

549

6

531

6

13TK51‐07

497

0.19

0.72812

0.01089

0.08839

0.00109

0.05976

0.00040

0.02467

0.00093

546

6

595

14

555

6

546

6

13TK51‐09

196

0.52

0.79191

0.01458

0.09288

0.00120

0.06184

0.00055

0.02525

0.00103

573

7

669

18

592

8

573

7

13TK51‐10

333

0.32

0.73255

0.01151

0.08808

0.00110

0.06033

0.00043

0.02552

0.00105

544

7

615

15

558

7

544

7

13TK51‐12

366

0.37

0.72512

0.01146

0.08713

0.00109

0.06037

0.00043

0.02540

0.00110

539

6

617

15

554

7

539

6

13TK51‐13

265

0.24

0.74731

0.01177

0.09074

0.00113

0.05973

0.00042

0.03091

0.00119

560

7

594

14

567

7

560

7

13TK51‐14

399

0.12

0.75781

0.01139

0.09095

0.00113

0.06043

0.00040

0.02823

0.00114

561

7

619

13

573

7

561

7

13TK51‐15

714

0.19

0.73914

0.01074

0.09154

0.00113

0.05857

0.00037

0.02824

0.00115

565

7

551

13

562

6

565

7

13TK51‐16

477

0.10

0.74282

0.01122

0.09142

0.00113

0.05894

0.00039

0.0267

0.00116

564

7

565

13

564

7

564

7

13TK51‐17

729

0.08

0.73337

0.01088

0.08973

0.00111

0.05928

0.00039

0.02911

0.0013

554

7

577

13

559

6

554

7

13TK51‐18

486

0.54

0.73423

0.01126

0.09045

0.00113

0.05888

0.00040

0.02865

0.00129

558

7

563

14

559

7

558

7

13TK51‐19

565

0.87

0.74946

0.01146

0.09185

0.00114

0.05919

0.00040

0.02905

0.00136

566

7

574

14

568

7

566

7

13TK51‐20

512

0.09

0.74657

0.01099

0.09088

0.00112

0.05958

0.00039

0.03038

0.00121

561

7

588

13

566

6

561

7

13TK51‐21

530

0.09

0.74381

0.01452

0.09127

0.00112

0.05911

0.00064

0.02823

0.00034

563

7

571

22

565

8

563

7

13TK51‐22

544

0.11

0.73312

0.01163

0.08962

0.00112

0.05933

0.00042

0.03168

0.00134

553

7

579

14

558

7

553

7

13TK51‐23

385

0.11

0.7655

0.01275

0.08946

0.00113

0.06206

0.00047

0.02574

0.00116

552

7

676

15

577

7

552

7

13TK51‐24

880

0.09

0.7449

0.01081

0.0910

0.00112

0.05937

0.00038

0.02975

0.00127

561

7

581

13

565

6

561

7

13TK54 (wt. Mean age =544±4 (2σ), n=21) 13TK54‐01

361

0.3

0.69330

0.01079

0.08797

0.00114

0.05716

0.00039

0.02731

0.00095

544

7

498

15

535

6

544

7

13TK54‐02

420

0.13

0.70548

0.01078

0.08983

0.00116

0.05696

0.00038

0.02658

0.00098

555

7

490

14

542

6

555

7

13TK54‐03R

517

0.17

0.68929

0.01040

0.08759

0.00113

0.05708

0.00038

0.02694

0.00101

541

7

495

14

532

6

541

7

0.15

0.70665

0.01057

0.08905

0.00114

0.05756

0.00038

0.02859

0.00112

550

7

513

14

543

6

550

7 7

13TK54‐05

544

13TK54‐07

470

0.1

0.68154

0.01053

0.08874

0.00115

0.05571

0.00038

0.02704

0.00118

548

7

441

15

528

6

548

13TK54‐08

342

0.57

0.75986

0.01189

0.08893

0.00115

0.06197

0.00043

0.02968

0.00124

549

7

673

14

574

7

549

7

13TK54‐09

516

0.11

0.70183

0.01072

0.08953

0.00115

0.05686

0.00038

0.03672

0.00166

553

7

486

14

540

6

553

7

13TK54‐11

596

0.13

0.71176

0.01090

0.09000

0.00116

0.05736

0.00039

0.02883

0.00140

556

7

505

14

546

6

556

7

14TK54‐15

439

0.12

0.72719

0.01215

0.08778

0.00106

0.06009

0.00047

0.02599

0.00134

542

6

607

16

555

7

542

6

14TK54‐16

305

0.25

0.70183

0.01089

0.08577

0.00107

0.05935

0.00041

0.02735

0.00102

530

6

580

15

540

6

530

6

13TK54‐18

248

0.48

0.71745

0.01160

0.08879

0.00111

0.05861

0.00043

0.02888

0.00118

548

7

553

15

549

7

548

7

13TK54‐19

363

0.10

0.69419

0.01075

0.08703

0.00108

0.05785

0.00040

0.02561

0.00109

538

6

524

15

535

6

538

6

13TK54‐20

286

0.54

0.70747

0.01145

0.08804

0.0011

0.05828

0.00043

0.03114

0.00136

544

7

540

16

543

7

544

7

13TK54‐21

483

0.14

0.71534

0.01764

0.08631

0.00106

0.06011

0.00104

0.02665

0.00032

534

6

608

36

548

10

534

6

13TK54‐22

560

0.42

0.71181

0.01092

0.08875

0.0011

0.05818

0.00040

0.02808

0.00126

548

7

537

14

546

6

548

7

13TK54‐24

310

0.19

0.73432

0.01197

0.08748

0.0011

0.06089

0.00045

0.02808

0.00136

541

7

635

15

559

7

541

7

13TK54‐25

597

0.09

0.71654

0.01009

0.08896

0.00109

0.05842

0.00036

0.02994

0.00100

549

6

546

12

549

6

549

6

13TK54‐26

563

0.13

0.76147

0.01655

0.08938

0.00111

0.06179

0.00079

0.02751

0.00033

552

7

667

25

575

10

552

7

13TK54‐27

545

0.11

0.72998

0.01049

0.08799

0.00108

0.06017

0.00038

0.02923

0.00103

544

6

610

13

557

6

544

6

13TK54‐28

457

0.15

0.69251

0.01019

0.08530

0.00105

0.05888

0.00038

0.02636

0.00095

13TK54‐29

598

0.11

0.72824

0.01053

0.08782

0.00108

0.06014

0.00038

0.02855

0.00107

528 543

6 6

563 609

13 13

534 556

6 6

528 543

6 6

Note: Zircon U‐Pb isotopes were measured using a Laser‐ablation ICP‐MS at the Department of Geosciences, National Taiwan University, Taipei, Taiwan. Detailed analytical procedures are described by Chiu et al. (2009).

Table 3  In situ zircon Lu‐Hf isotopic data of the Pütürge augen gneisses. spot

U 

Age (Ma)

(ppm)

176

Th/U

Yb

177

Hf

176

2σ

177

Lu Hf

176

2σ

177

Hf Hf

176

2σ

177

Hf

Hf i

εHf(T)

TDM (Ma)

TDMC (Ma)

13TK51 1

539

6

546

0.10

0.065

0.0008

0.0026

2.80E‐05

0.282473

1.90E‐05

0.2824

0.4

1151

1474

2

529

6

375

0.21

0.033

0.0001

0.0013

5.30E‐06

0.282454

1.80E‐05

0.2824

‐0.1

1139

1495

4

541

6

638

0.30

0.039

0.0002

0.0016

6.90E‐06

0.282422

1.80E‐05

0.2824

‐1.1

1194

1567

5

542

6

553

0.50

0.042

0.0004

0.0016

1.40E‐05

0.282379

2.00E‐05

0.2824

‐2.6

1255

1662

6

531

6

497

0.19

0.047

0.0011

0.0019

4.60E‐05

0.282495

2.20E‐05

0.2825

1.2

1096

1413

7

546

6

196

0.52

0.06

0.0002

0.0024

5.90E‐06

0.282461

1.90E‐05

0.2824

0.1

1163

1494

9

573

7

366

0.37

0.028

0.0001

0.0011

2.00E‐06

0.282361

2.30E‐05

0.2823

‐2.3

1261

1671

10

544

7

265

0.24

0.033

0.0005

0.0013

1.80E‐05

0.282414

1.80E‐05

0.2824

‐1.2

1195

1576

12

539

6

714

0.19

0.02

0.0002

0.0008

5.20E‐06

0.282439

1.70E‐05

0.2824

‐0.2

1144

1510

13

560

7

477

0.10

0.048

0.0003

0.0019

1.20E‐05

0.282436

4.70E‐05

0.2824

‐0.3

1182

1531

14

561

7

729

0.08

0.052

0.0002

0.002

7.30E‐06

0.282437

1.80E‐05

0.2824

‐0.3

1187

1532

15

565

7

486

0.54

0.06

0.0012

0.0024

4.20E‐05

0.28231

2.50E‐05

0.2823

‐4.8

1383

1822

16

564

7

565

0.87

0.05

0.0002

0.0019

1.00E‐05

0.282408

1.70E‐05

0.2824

‐1.2

1223

1590

17

554

7

512

0.09

0.075

0.0011

0.0029

3.90E‐05

0.28233

3.20E‐05

0.2823

‐4.5

1372

1794

18

558

7

530

0.09

0.061

0.0003

0.0023

6.50E‐06

0.282439

2.30E‐05

0.2824

‐0.4

1192

1535

19

566

7

544

0.11

0.051

0.0008

0.002

3.20E‐05

0.282411

1.90E‐05

0.2824

‐1.1

1223

1586

20

561

7

385

0.11

0.053

0.0003

0.0021

1.30E‐05

0.282353

2.70E‐05

0.2823

‐3.3

1309

1720

21

563

7

880

0.09

0.051

0.0005

0.002

2.00E‐05

0.282399

1.90E‐05

0.2824

‐1.6

1241

1615

22

553

7

546

0.10

0.058

0.0004

0.0023

1.20E‐05

0.282463

2.20E‐05

0.2824

0.4

1158

1484

23

552

7

375

0.21

0.051

0.0003

0.002

1.40E‐05

0.282396

1.80E‐05

0.2824

‐1.9

1245

1629

24

561

7

432

0.11

0.063

0.0007

0.0025

2.70E‐05

0.282369

2.30E‐05

0.2823

‐2.9

1301

1695

1

544

7

361

0.30

0.024

0.0002

0.0009

7.50E‐06

0.282444

2.50E‐05

0.2824

0

1142

1500

2

555

7

420

0.13

0.04

0.0007

0.0016

2.30E‐05

0.28243

2.00E‐05

0.2824

‐0.4

1180

1539

3R

541

7

544

0.15

0.045

0.0002

0.0018

9.00E‐06

0.282391

2.80E‐05

0.2824

‐2.2

1242

1639

5

550

7

470

0.10

0.051

0.0006

0.002

2.10E‐05

0.282438

2.00E‐05

0.2824

‐0.4

1184

1535

7

548

7

516

0.11

0.048

0.0002

0.0019

9.60E‐06

0.28232

3.00E‐05

0.2823

‐4.6

1349

1796

8

549

7

596

0.13

0.028

0.0005

0.0011

2.30E‐05

0.282368

1.90E‐05

0.2824

‐2.6

1253

1670

9

553

7

439

0.12

0.027

0.0003

0.0011

1.40E‐05

0.282327

4.00E‐05

0.2823

‐4

1310

1760

11

556

7

248

0.48

0.051

0.0006

0.0021

1.80E‐05

0.282303

2.20E‐05

0.2823

‐5.1

1378

1833

15

542

6

560

0.42

0.052

0.0005

0.002

1.80E‐05

0.28236

1.70E‐05

0.2823

‐3.4

1297

1715

16

530

6

310

0.19

0.022

0.0003

0.0009

1.10E‐05

0.282416

1.90E‐05

0.2824

‐1.3

1180

1571

18

548

7

563

0.13

0.032

0.0004

0.0012

1.50E‐05

0.282312

3.10E‐05

0.2823

‐4.7

1337

1800

19

538

6

545

0.11

0.036

0.0002

0.0015

7.60E‐06

0.282416

2.20E‐05

0.2824

‐1.3

1198

1579

20

544

7

457

0.15

0.026

0.0004

0.001

1.40E‐05

0.2824

2.20E‐05

0.2824

‐1.5

1204

1599

21

534

6

598

0.11

0.044

0.0002

0.0018

6.40E‐06

0.282399

2.10E‐05

0.2824

‐2

1230

1624

22

548

7

361

0.30

0.051

0.0004

0.002

1.30E‐05

0.282348

2.70E‐05

0.2823

‐3.7

1313

1737

24

541

7

517

0.17

0.045

0.0007

0.0018

2.60E‐05

0.282303

3.00E‐05

0.2823

‐5.3

1369

1836

25

549

6

544

0.15

0.058

0.0004

0.0023

1.50E‐05

0.282377

1.80E‐05

0.2824

‐2.7

1281

1678

26

552

7

470

0.10

0.063

0.0000

0.0024

2.90E‐06

0.282398

2.00E‐05

0.2824

‐2

1256

1633

27

544

6

342

0.57

0.054

0.0003

0.0021

9.20E‐06

0.282447

1.90E‐05

0.2824

‐0.3

1175

1521

28

528

6

516

0.11

0.034

0.0007

0.0014

2.60E‐05

0.28234

2.20E‐05

0.2823

‐4.1

1301

1751

29

543

6

596

0.13

0.063

0.0005

0.0025

1.90E‐05

0.282326

2.50E‐05

0.2823

‐4.7

1363

1800

13TK54

Notes: zircon Lu‐Hf isotopes were measured using a Neptune multi‐collector ICP‐MS equipped with a Lambda Physik COMpex UV‐193 laser‐ablation system at the Institute of Geology and Geophysics, Chinese Academy of Sciences in Beijing, China. Detailed analytical procedures are described by Wu et al. (2006). Lu‐Hf isotopic calculations are made with following equations: λ Lu‐Hf  = 1.86 × 10‐11 y (Scherer et al., 2001) εHf(T)=[(

T 176 T 177 4  Hf)Sample /( Hf/ Hf)CHUR ‐1] x 10 (Patchett and Tastumoto, 1981) T 176 0 176 0 T 176 0 176 0 177 177 λT 176 177 177 177 λT ( Hf/ Hf)Sample =( Hf/ Hf)Sample ‐( Lu/ Hf)Sample  x (e ‐1); ( Hf/ Hf)CHUR =( Hf/ Hf)CHUR ‐( Lu/ Hf)CHUR  x (e ‐1) 0 0 176 177 176 177 ( Hf/ Hf)CHUR =0.282772; ( Lu/ Hf)CHUR  =0.0332  (Blichert‐Toft and Albarede, 1997) 176 177 176 177 ( Hf/ Hf)DM=0.28325; ( Lu/ Hf)DM =0.0384  (Nowell et al., 2000; Griffin et al., 2000) 176 177  ( Lu/ Hf)mean crust =0.015  (Griffin et al., 2000) 176

176

Hf/

177

177

f CC  = (0.015/0.0332)‐1 = ‐0.5482 ; f DM  = (0.0384/0.0332)‐1 = 0.1566

Highlights

in situ zircon U–Pb dating and Lu-Hf isotope analyses of the Granitic gneisses of the Pütürge Metamorphic massif( Southest Anatolian, Turkey) have been studied for the first time. The U-Pb ages (551-544Ma) correspond to the Ediacaran-Early Cambrian In situ zircon Hf isotopes data indicate a magmatic sources from ca.1.8-1.4 Ga The magmatic rocks are related to Cadomian- Early Cabrian magmatism along the active margin of Gondwana